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Palaeoecological evidence of agricultural activity and human impact on the environment at the ancient settlement centre of Keava, Estonia/Muistsed loodusolud ja inimtegevuse moju looduskeskkonnale--paleookoloogiline andmestik Keava asustuskeskusest.

INTRODUCTION

The scarcity of archaeological artefacts and complexity of interpretation of such sources of information often make it necessary to collaborate in an interdisciplinary manner. Palaeoecological investigations, particularly pollen analysis, have greatly contributed to our knowledge of prehistoric environments and the manner in which human activity affected them (e.g. Veski 1998; Poska 2001; Poska et al. 2004). In Estonia long and well-established co-operation traditions have existed between palaeoenvironmental scientists and archaeologists (Veski & Lang 1996; Veski et al. 2005a) already since the times of Paul Thomson and Richard Indreko in the 1920s. Being one of the pioneers of the palynological analysis method, Thomson initiated a viable and continued tradition of palynological research in Estonia. In addition to describing post-glacial vegetation history on pollen assemblages from peat and lake sediments (e.g. Thomson 1929), he also applied pollen analyses in archaeological investigations (Thomson 1928).

However, quite often prehistoric settlements and other finds of archaeological source material and possible sediment archives, such as deposits of small-sized lakes and mires that mostly trap local natural and man-made environmental signals like wind-dispersed pollen grains, fire-induced microscopic charcoal particles, and erosion-generated soil dust particles, are located too far from each other. More local pollen signals can only be detected by investigations at small-scale sites (Brostrom et al. 1998; Veski et al. 2005b; Poska et al. 2008). Keava, an ancient population centre with three settlement sites and two hillforts within the radius of 1 km, which were investigated by archaeological excavations conducted by Prof. Valter Lang, University of Tartu, during 2001-04, are located very close to small basins filled with sediments suitable for palaeoenvironmental studies.

Keava hillforts and settlements are located in Rapla County, 60 km south of Tallinn. Linnaaluste settlement is one of the largest Viking Age villages in the Baltic countries and definitely was an important centre in the past. For instance, chronicles mention the siege of Keava fortification by Prince Izyaslav of Novgorod in 1054. The German crusaders forced the hillfort to surrender during one of their raids in early 1224.

We have performed palaeoecological studies of sediment cores from two small mires, Verevainu and Linnaaluste, which are located in the immediate neighbourhood of the archaeological sites, where previous pollen studies or other palaeoecolocigal investigation are still lacking. Moreover, detailed pollen diagrams, which could reflect early indications of human impact on the environment, are absent from most of the inland areas of central Estonia.

The study seeks (1) to determine whether there exists earlier palaeoecological evidence of the presence of man at Keava as the archaeological dataset shows and (2) to follow the land-use history and human impact on local environment using pollen, charcoal, and loss-on-ignition analysis and [sup.14]C chronology of two peat sequences with combination of the results of archaeological excavations.

GEOLOGICAL SETTING OF THE STUDY SITE

The configuration of the topography in the Keava area is closely associated with the retreat of the Weichselian ice sheet around 13 300 calendar years ago (Kalm 2006). The Keava-Esku esker (Fig. 1), a 2 km long ridge extending from south to north, is a striking landform of fluvioglacial origin, supposedly formed by in-glacier streams in ice-walled tunnels near the ice margin. The relative height of the esker is up to 17 m (altitude above sea level up to 86 m). The ancient steep-walled and flat-topped Keava hillfort is situated in the southern part of the esker. As seen from the nearby gravel-pit, the esker is formed of sand and overlying gravel.

East of the esker lies the large Keava Bog (surface area 1900 ha, maximum thickness of peat 8.8 m), the northwestern part of which is exploited for peat. The Quaternary deposits further westwards of the esker are dominated by tills and glaciolacustrine clays and sands. A coastal escarpment at an altitude of 73 m a.s.l. near Keava (Rahni 1976) is a firm evidence that waters of the Baltic Ice Lake inundated the study area, however, the highest parts of the esker formed a small-sized archipelago.

Besides the large Keava Bog, several minor hollows with peat infilling occur in the vicinity of the Keava settlement centre. One of them is located at the foot of the Keava hillfort just north of Linnaaluste I settlement. The former mire (58[degrees]57'03"N; 24[degrees]56'48"E; Fig. 1) with a size of 100 m x 150 m, which we call Verevainu Mire, is drained, reclaimed, and transformed into pasture, whereas the edge of the fen close to the hillfort is overgrown with bushes of alder and willow. The topmost peat layer has been destroyed during land amelioration works and desiccation/oxidation of the peat has resulted from the drainage of the peat bog. In addition to the proximity to the Keava hillfort, Verevainu Mire lies less than 100 m from other archaeologically significant Early Viking Age/Viking Age settlements Linnaaluste I and III (Fig. 2).

As the record covering the last thousand years of the Verevainu Mire peat sequence has been destroyed due to ditching and land amelioration, a second peat sequence from the mire that we call Linnaaluste Mire was chosen for investigation to complement the missing upper part of the Verevainu Mire. The Linnaaluste Mire (58[degrees]57' 11 "N; 24[degrees]57'00"E; Fig. 1) is situated 300 m north of the Keava hillfort. This small oval-shaped mire with a size of 80 m x 150 m is today covered with pine forest.

METHODS

In July 2002, a set of replicate sediment cores was taken from the Verevainu Mire using a 7.5 cm diameter and 1 m long Russian peat sampler. Sediments down to the bottom were recovered, maximum sediment thickness of 3.88 m was recorded, sediment cores were described, photographed, carefully packed into 1 m plastic semi-tubes, wrapped in polyethylene film, labelled, and transported to the laboratory. Additional parallel cores were taken for radiocarbon analysis. In September 2003, the sediment thickness of the Linnaaluste Mire was surveyed, a 1.62 m core was recovered, and sediment samples for stratigraphic analysis were taken.

[FIGURE 1 OMITTED]

[FIGURE 2 OMITTED]

Peat composition was determined by loss-on-ignition measurements. The sediment core of the Verevainu Mire at a depth of 18-130 cm was sectioned into consecutive 2 cm subsamples and the whole core of the Linnaaluste Mire was cut into 2 cm segments. The subsamples were dehydrated at 100 [degrees]C for 24 h, weighed, then combusted at 550 [degrees]C for 4 h and re-weighed to determine the organic content of the peat and ignition residue (IR), i.e. the mineral content of the peat.

Samples for pollen analysis were processed using standard procedures (Berglund & Ralska-Jasiewiczowa 1986). Known quantities of Lycopodium spores were added prior to digestion to permit calculation of pollen concentration and accumulation rates (Stockmarr 1971). The sample residue was then mounted on microscope slides with glycerol. Pollen grains were routinely counted and identified at 320 x magnification; for determination of cereal pollen grains 1000 x magnification, oil immersion, and phase contrast were used. Pollen grains were identified to the lowest possible taxonomic level using the reference collection held at the Institute of Geology at Tallinn University of Technology and published pollen keys (e.g. Fsgri & Iversen 1989; Reille 1992). A minimum of 500 grains were counted in each sub-sample. Pollen percentages were calculated as in Veski (1998), and pollen diagrams were compiled and plotted using the TILIA and TILIA-GRAPH software (Grimm 1990, 2004).

The pollen slides were also examined for microscopic charcoal particles. Two different charcoal size groups were distinguished--the 10-100 um and >100 urn fractions.

The chronology of the Verevainu Mire core is based on three conventional radiocarbon dates and that of the Linnaaluste Mire on two conventional [sup.14]C dates. All dates were obtained from 5 cm thick bulk ombrotrophic peat samples. The radiocarbon dates were converted to calendar years using the IntCal04 calibration dataset (Reimer et al. 2004) and OxCal 4.0 program deposition model (Bronk Ramsey 2001, 2008) with the 2[sigma] (95.4% confidence) level. In order to construct an age--depth model, weighted average estimates of the probability distributions of the calibrated age were calculated. All ages mentioned in this text are given in calendar years BC or AD.

LITHOSTRATIGRAPHY AND DATINGS

The stratigraphy for the two studied sites is described in Table 1. The basal minerogenic sediments in both mire depressions possibly deposited in the Baltic Ice Lake. A thin 12 cm layer of coarse detritus gyttja suggests that a shallow lake existed in the Verevainu basin before the limnic environment completely filled in and changed to telmatic environment, first as an open fen and thereafter as an ombrotrophic bog. Sediment stratigraphy of the Linnaaluste Mire revealed that the basin lacked the Early Holocene shallow limnic environment. Instead, peat deposition took place.

Altogether five radiocarbon datings were obtained, three from the Verevainu Mire and two from the Linnaaluste Mire (Table 2). The results from the Verevainu Mire showed that the uppermost 120 cm accumulated during the last ca 5500 calibrated years BP. The applied age-depth model showed that the average peat accumulation rate was 0.1 mm [yr.sup.-1] in the lower part, 0.2 mm [yr.sup.-1] in the middle part, and 0.4 mm [yr.sup.-1] in the upper part of the sediment sequence.

The datings from the Linnaaluste Mire sediment sequence indicate that the peat profile down to a core-depth of 95 cm covers approximately the last 8700 calibrated years BP, i.e. point to the fact that the origin of this basin is not related to the Subatlantic wet conditions as we expected, but is much older and almost covers the entire post-glacial period. Owing to the very low sedimentation rate (less than 0.1 mm [yr.sup.-1]) and therefore poor resolution of the record, we could not use that sediment sequence for complementing the missing subsurface archive of the Verevainu Mire for the last thousand years in a proper way.

VEGETATION AND LAND USE HISTORY

The environmental and general vegetation history, with special emphasis on the impact of human habitation of the Keava area, is mostly based on the pollen diagrams (Figs 3, 4) and IR curve (Fig. 5) from the ancient Verevainu Mire, covering the time-span from 3500 BC to about AD 1500 (IR) and from 2200 BC to about AD 600 (pollen). Additional information on vegetation history is based on pollen evidence from the Linnaaluste Mire (Fig. 6).

From about the Late Neolithic ca 2000 BC, the Keava area was forested and mixed forest of Betula (birch), Pinus (pine), and Picea (spruce) grew on dry ground, whereas Alnus (alder) formed alder thickets around the Verevainu (Fig. 3) and Linnaaluste mires on wet ground (Fig. 6). Broad-leaved trees, particularly Quercus (oak), Corylus (hazel), and Tilia (lime), were more abundant than today but rather rare. In general, the pollen diagrams indicate very low non-tree pollen values (herbs) without any evident changes. Moreover, the tree pollen curves do not show any apparent disturbances of the forest cover and imply that there was no particular human impact and agriculture in the nearest vicinity of the studied area. The tree pollen accumulation rate was also high, indicating closed conditions.

[FIGURE 3 OMITTED]

[FIGURE 4 OMITTED]

[FIGURE 5 OMITTED]

In small ombrotrophic Sphagnum-dominated peat bogs deposition of mineral particles often reflects soil erosion associated with human activity in the vicinity of the bog (e.g. Vuorela 1983; Dorfler 1992). Mineral material originates from particles transported by wind and rain and consists mainly of particles derived from eroding soils. Smaller peat bogs closer to cultivated fields have greater ability to trap mineral soil influx arising from human-induced soil erosion. Therefore peat profiles of small-sized bogs are expected to be especially suitable for the investigation of ancient human agricultural activity. Ombrotrophic peat bogs, dominated by Sphagnum mosses, are solely fed by atmospheric deposition, i.e. they receive all of their water, nutrients, and mineral particles from precipitation falling directly on their surfaces. Ombrotrophic peat studies in Estonia have shown that in natural conditions the content of organic matter in Sphagnum-dominated bogs is very high and regular, whereas the proportion of mineral matter is low, less than 5%. In transitional bog peat IR values are slightly higher, 5-10% (Valk 1988). We have to consider that the past Verevainu Mire was similar to the transitional type of bogs, therefore it was not solely fed by atmospheric deposition but also received moisture by means of groundwater seepage from the slopes of the esker. In the Verevainu Mire peat sequence from about 3500 BC to ca 1100 BC the IR values are low (7-8%) and fluctuations are lacking (Fig. 5), thus additionally implying native forests without any clearings of woodland and mineral soil influx arising from soil erosion induced by ancient agricultural activity.

[FIGURE 6 OMITTED]

The first single cereal pollen finds (Fig. 4) of Triticum-type (wheat) pollen appeared during the Early Bronze Age ca 1500 BC together with cultural indicators such as apophytes Artemisia (wormwood) and Taraxacum type (dandelion). The pollen evidence suggests that small-scale attempts at crop tillage may have been made, but the human population possibly living in the Keava area was scarce and did not significantly influence the plant cover structure and local environment. In addition, an isolated find of an Early Bronze Age bronze axe (Jaanits et al. 1982) from Lelle, ca 10 km south of the study area, implies preferably a small and highly dispersed human population in the area rather than the absence of people.

Recent records of Triticum-type pollen accompanied by Cannabis-type (hemp) pollen ca 5600 BC at Akali, middle eastern Estonia, by Poska & Saarse (2006) can be interpreted as the first possible traces of the acquaintance of foragers with crop farming through contacts with southern European agrarian tribes already in the Late Mesolithic. During the Bronze Age, crop cultivation already played an important role in the farming economy in northern Estonian coastal alvar areas, e.g. in Maardu (Poska et al. 2004), Kahala (Poska & Saarse 1999), and Mustjarve (Veski 1998). However, the inland parts of northern and central Estonia were obviously economically marginal areas during the Bronze Age. The first sporadic finds of cereal pollen grains, namely Triticum and Avena type (oat) were detected in the pollen diagram from Ruila, ca 40 km northwestwards of Keava in the early Bronze Age ca 1500 BC (Poska & Saarse 2002), i.e. at the same time as in Keava.

The Verevainu Mire pollen diagram indicates that the landscape around Keava remained constantly forested primarily with birch, pine, and spruce trees without considerable fluctuations in the tree population, arboreal pollen accumulation, and disturbances in the woodland structure until 350 BC, followed by an abrupt change in the pollen record. A sharp and persistent rise in total herb pollen percentage and somewhat higher herb pollen accumulation with corresponding decrease in the tree pollen accumulation possibly suggest degeneration of forests and a change towards partially open landscape. Not only a decrease in tree pollen percentage was seen, but also tree pollen accumulation rates reduced 2-3 times, indicating major ecological changes in the vicinity of Keava, recession of forest, and opening of the landscape. The distribution of non-tree vegetation and opening up of the landscape were evidently reached by clearance combined with the effects of fire, as indicated by high values of charcoal particles. Somewhat earlier, at ca 600 BC, the pollen curve of cereals contains only few grains of Triticum type. However, the curve remains unbroken, pointing to crop cultivation at least in limited areas close to the Verevainu Mire and is likely associated with the appearance of permanent fields (Lang 1994). The pollen evidence also has additional clear signs of human activities, such as Artemisia, Chenopodiaceae (goosefoot family), ruderals, Plantago types (plantains), and Juniperus (juniper), suggesting creation of pastures, forest grazing, and onset of the formation of an agrarian landscape at Keava in the Early Pre-Roman Iron Age (Fig. 5).

The deforestation and opening up of landscape leading to reduction in plant cover may have contributed to topsoil disturbances and increased erosion intensity. However, the mineral content of the peat of the Verevainu Mire starts to increase and a rise in IR values is steady somewhat earlier than observed in the pollen evidence, from around 1000 BC (Fig. 5), which might indicate elevated fluxes of soil dust resulting from man-induced soil erosion. The earlier indication of human interference, detected more sensitively by the erosion signal rather than by pollen evidence, may result from the relatively coarser sampling interval employed for pollen analyses than for loss-on-ignition analyses of the Verevainu Mire profile, as well as from the fact that early cultivation signals are very weak.

The pollen evidence from the Linnaaluste Mire (Fig. 6) in general mimics that from the Verevainu site, only the Pre-Roman Iron Age human impact was slightly weaker, the signal of microscopic charcoal was insubstantial, and no major changes occurred in the tree cover. These features suggest that possibly the Linnaaluste basin was a bit too far away from the main human activities and the proximate edge of the mire remained forested, filtering the pollen signal.

Recent archaeological discoveries at a nearby fortification site of Vonnumagi, namely five radiocarbon dates on charcoal and finds of coarse-grained and striated ceramics, suggest that the hillfort is of Pre-Roman Iron Age (Lang et al. 2005). Although settlement layers of that age in Keava are still controversial, we assume that hillforts were not erected in uninhabited areas and people settled in the region, which is inconsistent with the timing of increased arable and pastoral farming evidence during the Pre-Roman Iron Age in the Verevainu pollen diagram. Moreover, recent archaeological field surveys have revealed several settlement sites, such as Kabikula and Koogimae, in the vicinity of Keava that presumably date from the same period (Lang & Konsa 2004). Both archaeological and palaeoecological evidence implies colonization of former marginal lands in the Keava area and suggests implementation of crop farming, exploitation of landscape, and significant change in the natural vegetation composition during the Pre-Roman Iron Age around 350 BC. Moreover, this is consistent with an earlier consideration that the cereal cultivation had expanded spatially into more extensive areas in inland Estonia by the Iron Age (Poska et al. 2004; Saarse et al. 2010).

The overall impression from the pollen and soil erosion data implied only insignificant expansion of agricultural activities from 350 BC to AD 300. However, around AD 300 the pollen record provided distinct evidence of increase in both arable and pastoral farming activity in the area. The landscape in the vicinity of Keava was progressively cleared, as tree pollen decreased notably and herb pollen increased. Herbaceous pollen that was recorded at higher frequencies includes mainly Cyperaceae, Poaceae, but also Rumex (sorrel), Taraxacum and others, as well as indicators of grazing like Juniperus and Pteridium (ferns), which may hint at pastoral farming. Pollen evidence for arable farming continued to increase as an abrupt rise in cereal pollen in the pollen diagram, which showed intensified cultivation farming. Moreover, new crops, such as Secale (rye) and Hordeum (barley), were introduced. These changes coincided with a short-lived peak of microscopic charcoal, which might have resulted from slash and burn close to the study site. Throughout this period, which lasted from AD 300 to 600, microscopic charcoal was present at very high values; in addition, charcoal occurred in macroscopic form, which suggested very local origin.

The comparison of the IR curve with the respective human-impact indicators in the pollen record from the study site showed a clear link to human land use at the time of IR peaks. The IR content continued to increase until AD 350 and afterwards, showing that the topsoil erosion and wind-blown accumulation of mineral dust particles in the Verevainu Mire had drastically increased. The data suggest considerable deforestation and destruction of vegetation, and the increasing intensity of agricultural practices in the Late Roman Iron Age, in the Migration Period, and in the Pre-Viking Age.

The topmost subsurface sediment record of the Verevainu Mire was visibly disturbed and therefore pollen analysis further upwards was not performed. In addition, the irregular shape of the IR curve after AD 1000 should be interpreted with some caution. However, judging in particular from the rising percentage of charcoal in the Linnaaluste Mire sediment record (Fig. 6), extensive deforestation and expansion of arable farming during the Viking Age and in the early 13th century can be expected.

In contrast to the earlier periods, there are abundant Pre-Viking Age, Viking Age, and later archaeological sites at Keava. These include the second, third, and fourth cultural layers from the Keava hillfort (Lang & Konsa 2004) and Linnaaluste I and III settlements (Konsa et al. 2002, 2003), which were all established very close to the Verevainu Mire. A large settlement of Linnaaluste I was established during the Pre-Viking Age in the 7th-8th centuries. A Linnaaluste III iron workshop probably operated during the same period (Lang & Konsa 2004), that is somewhat later than revealed by the available palaeoecological material. However, the burning event of the initial Keava fortification, dated to 1560 [+ or -] 60 [sup.14]C years, i.e. AD 360-640 (Lang et al. 2004), was almost consistent with the enhanced human interference in the Verevainu Mire sediment record.

CONCLUSIONS

Pollen, charcoal, and loss-on-ignition analyses from the peat section located in the immediate neighbourhood of the ancient settlement centre of Keava revealed the local history of vegetation and clear evidence of human-induced disturbances on the environment. From about 2000 BC, natural birch-pine-spruce forest cover surrounded the Keava area. The first Triticum pollen grain at ca 1500 BC points to the earliest date for the arrival of agriculture in the Keava area, however human population possibly living there was small and did not influence the local environment. Pollen data combined with the high values of charcoal particles suggest forest clearance, opening of landscape, and cultivation of cereals and thus provide convincing evidence of the increasing population and expansion of agriculture during 600-300 BC, however, peat IR values as an indicator of topsoil erosion started to increase even earlier, from around 1000 BC. Following a certain period of standstill in human-induced impact on the environment, the indicators of sediment record disturbance inferred a new major expansion of arable farming at AD 300-600. The high anthropogenic impact on the landscape, evidenced by the palaeoecological record during the Pre-Roman Iron Age and the Late Roman Iron Age/Migration Period, distinctly predates extensive archaeological settlement data until the Pre-Viking Age.

doi: 10.3176/earth.2010.1.06

Acknowledgements. Funding for this research was provided by the Estonian Ministry of Education and Research (SF0332710s06) and the Estonian Science Foundation (grant No. 6995). Helerin Heinsalu helped in the coring and measured loss-on-ignition on samples from the Verevainu Mire. Holger Koot analysed several sediment samples from the Linnaaluste Mire for pollen and loss-on-ignition as part of his Bachelor studies. Dr Laimdota Kalnina and an anonymous reviewer are thanked for constructive comments and suggestions on the manuscript.

Received 14 April 2009, accepted 27 August 2009

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Atko Heinsalu and Siim Veski

Institute of Geology at Tallinn University of Technology, Ehitajate tee 5, 19086 Tallinn, Estonia; heinsalu@gi.ee
Table 1. Lithostratigraphy of the sediment sequences from the
Verevainu and Linnaaluste mires

Depth from
the surface,
cm             Sediment description

               Verevainu Mire

0-15           Humus, dark
15-35          Sphagnum peat, dark brown, in the lower boundary sand
                 grains, probably sediment mixed during land
                 amelioration
35-77          Sphagnum peat, brown, poorly decomposed
77-170         Wood-Sphagnum peat, dark brown, fairly decomposed,
                 0.1-0.2 cm thick charcoal layers at 101, 96,
                 and 81 cm
170-210        Wood-Phragmites peat, brown, poorly decomposed
210-277        Fen moss peat, light brown, poorly decomposed
277-339        Phragmites peat, brown, fairly decomposed
339-351        Gyttja, greenish-brown, abundant coarse detritus
351-388        Silt, greyish-green

               Linnaaluste Mire

7-27           Sphagnum peat, brown, fairly decomposed
27-96          Eriophorum-Sphagnum peat, dark brown, fairly
                 decomposed, 0.1-0.2 cm thick charcoal layers at
                 81, 62, 56, 50, 46, 42, 38, 35, and 27 cm
96-138         Peat, almost completely decomposed
138-144        Silt with organic material, grey
144-162        Silt, grey

Depth from
the surface,
cm             Environment

               Verevainu Mire

0-15           Drained and reclaimed peat bog
15-35          Treeless transitional bog
35-77          Treeless transitional bog
77-170         Forested transitional bog
170-210        Forested swamp
210-277        Open fen
277-339        Open fen
339-351        Shallow lake
351-388        Baltic Ice Lake?

               Linnaaluste Mire

7-27           Mire
27-96          Mire
96-138         Mire
138-144        Baltic Ice Lake?
144-162        Baltic Ice Lake?

Table 2. Radiocarbon datings from the studied peat sequences at Keava

Depth from
the surface,   Laboratory    [sup.14]C age,      Calibrated age,
cm             code          years BP            95.4% probability

                                                 Verevainu Mire

55-60          Tln-2727      1590 [+ or -] 55    AD 345-595
80-85          Tln-2726      2465 [+ or -] 60    BC 765-410
115-120        Tln-2728      4455 [+ or -] 55    BC 3345-2930

                                                 Linnaaluste Mire

46-52          Tln-2756      3690 [+ or -] 70    BC 2285-1895
90-96          Tln-2755      7855 [+ or -] 85    BC 7035-6510

Depth from
the surface,
cm             Archaeological period

55-60          Late Roman Iron Age/Migration Period
80-85          Early Bronze Age/Early Roman Iron Age
115-120        Middle Neolithic/Late Neolithic
46-52          Late Neolithic
90-96          Early Mesolithic
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Author:Heinsalu, Atko; Veski, Siim
Publication:Estonian Journal of Earth Sciences
Article Type:Report
Geographic Code:4EXES
Date:Mar 1, 2010
Words:5110
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